Turkish Journal of Earth Sciences Turkish J Earth Sci (2018) 27: 64-88 http://journals.tubitak.gov.tr/earth/ © TÜBİTAK Research Article doi:10.3906/yer-1707-9

Heavy minerals and exotic pebbles from the Eocene flysch deposits of the Magura Nappe (Outer Western Carpathians, eastern Slovakia): their composition and implications on the provenance

1, 2 † 3 Katarína BÓNOVÁ *, Ján BÓNA , Martin KOVÁČIK , Tomáš MIKUŠ 1 Institute of Geography, Faculty of Science, Pavol Jozef Šafárik University, Košice, Slovakia 2 Kpt. Jaroša 13, Košice, Slovakia 3 Earth Science Institute SAS, Geological Division, Banská Bystrica, Slovakia

Received: 10.07.2017 Accepted/Published Online: 15.11.2017 Final Version: 08.01.2018

Abstract: The study aims to reconstruct the crystalline parent rock assemblages of the Eocene Strihovce Formation (Krynica Unit) and Mrázovce Member (Rača Unit) deposits, based on the heavy mineral suites, their corrosive features, geochemistry of garnet and tourmaline, zircon cathodoluminescence (CL) images, and exotic pebble composition. Both units are an integral part of the Magura Nappe belonging to the Flysch Belt (Outer Western Carpathians). Corrosion signs observable on heavy minerals point to different burial conditions and/or diverse sources. The compositions of the detrital garnets and tourmalines as well as the CL study of zircons indicate their origin in gneisses, mica schists, amphibolites, and granites in the source area. According to observed petrographic and mineralogical characteristics, palaeoflow data and palaeogeographical situation during the Eocene may show that the Tisza Mega- Unit crystalline complexes including a segment of the flysch substratum could represent the lateral (southern) input of detritus for the Krynica Unit. The Rača Unit might have been fed from the northern source formed by the unpreserved Silesian Ridge. The Marmarosh Massif (coupled with the Fore-Marmarosh Suture Zone) is promoted to be a longitudinal source.

Key words: Eocene, Outer Western Carpathians, Magura Basin, exotic pebbles, heavy minerals, geochemistry, provenance

1. Introduction Previous provenance studies on the Palaeogene Heavy-mineral assemblages in the sediments can provide deposits from the eastern part of the Magura Nappe valuable information and thus serve as indicators of (Flysch Belt, Outer Western Carpathians) were focused on the palaeogeographic connections between individual either petrography of major framework grains (Ďurkovič, palaeogeographical domains (Michalík, 1993) on 1960, 1961, 1962) or on exotic pebble composition provenance reconstruction of ancient and modern clastic (Leško and Matějka, 1953; Wieser, 1967; Nemčok et al., sedimentary rocks (e.g., Morton, 1987; Morton and 1968; Marschalko, 1975; Oszczypko, 1975; Marschalko Hallsworth, 1999; Morton et al., 2004, 2005; Čopjaková et al., 1976; Mišík et al., 1991a; Oszczypko et al., 2006, et al., 2005; Oszczypko and Salata, 2005; Mange and 2016; Olszewska and Oszczypko, 2010). Based on heavy Morton, 2007). Chemical composition of heavy minerals mineral suites, the provenance has been also investigated is dependent on the parent rock composition and P/T (Ďurkovič, 1960, 1965; Starobová, 1962), and recently more conditions under which they originated (crystallisation, detailed results were reported from electron microprobe postmagmatic fluid attack, metamorphism). Some of analyses (e.g., Salata, 2004; Oszczypko and Salata, 2004, them are resistant to weathering, mechanical effects 2005; Bónová et al., 2016, 2017). of transport, and burial diagenesis in connection with New information on exotic pebbles, morphological intrastratal dissolution. Therefore, heavy minerals features of heavy minerals, garnet and tourmaline are usually excellent provenance indicators, ideally in geochemistry, and zircon cathodoluminescence analysis combination with palaeoflow analysis and investigation of obtained from the Eocene clastic deposits of the Mrázovce exotic pebbles (pebbles or fragments of rock, preserved in Member belonging to the Rača Unit (RU) and of the sandstones and conglomerates, comprising various rocks Strihovce Formation belonging to the Krynica Unit (KU) derived from the hypothetical or destroyed source area). are presented in this study. This is further supported by * Correspondence: [email protected] 64 BÓNOVÁ et al. / Turkish J Earth Sci the palaeoflow analysis, and the possible source material tectono-lithofacies units: the Krynica, Bystrica, and Rača of deposits is discussed. Our new data from the Strihovce units (Figures 1a and 1b). These units consist of deep-sea, Fm. are interpreted in the context of previous studies on mostly siliciclastic deposits of Late Cretaceous to Oligocene palaeoflow directions (Koráb et al., 1962; Nemčok et al., age. In the south, the Magura Nappe is tectonically 1968; Oszczypko, 1975; Kováčik et al., 2012) and exotic bounded by the Klippen Belt, while in the north-east it is pebble compositions (Marschalko et al., 1976; Mišík et in tectonic contact with the Dukla Unit belonging to the al., 1991a; Oszczypko et al., 2006). The aim of this paper Fore-Magura group of nappes (e.g., Lexa et al., 2000). is to review and reevaluate the published data, as well The Rača Unit represents the northernmost tectono- as to interpret the new results from petrographic and lithofacies unit of the Magura Nappe. Based on lithofacies mineralogical study of the Eocene deposits from the differences in its northern and southern parts, two zones Krynica and Rača units cropping out in the eastern part of are distinguished (Figure 1b, Kováčik et al., 2011, 2012): the Magura Nappe. the Outer Rača Unit (Siary Unit in the Polish OWC) and the Inner Rača Unit (Rača Unit s.s. in the Polish 2. Geological background and potential source areas of OWC). The Outer Rača Unit consists of the Beloveža Eocene deposits and Zlín formations. The Beloveža Fm. (Early Eocene – The Magura Nappe is the innermost tectonic unit of the Middle Eocene) is formed by thin-bedded flysch and Flysch Belt (Outer Western Carpathians, OWC). It is variegated claystones. The lower part of the Zlín Fm. subdivided (from the south to north) into three principal (Middle Eocene – Early Oligocene) is composed of the

21°0’0’’E 21°30’0’’E b a

study area

Topľa Svidník

Bardejov Ondava

Giraltovce 1 6 8 5 7

0 5 10 km ec Labor

2 Dukla Unit ’N

ocha Grybow Unit (Smilno tectonic window) 3 Cir

4 49°0’0’ Outer Rača (Siary) Unit Humenné E Inner Rača Unit N

Magura Nappe Paleotransport directions I Bystrica Unit A Krynica Unit Mrázovce Mb. R

Pieniny Klippen Belt Strihovce Fm. K

Neovolcanites (Middle-Upper Miocene volcanites) > 10 data ± 5 data U

Figure 1. a) DTM map showing the position of the studied area in Central Europe; b) simplified and partly modified structural sketch map of the NE part of the Slovak Flysch Carpathians (according to Stránik, 1965; Koráb, 1983; Nemčok, 1990; Žec et al., 2006; Kováčik et al., 2011; Bónová et al., 2017; http://mapserver.geology.sk/gm50js) with sampling locations (1 – GIR-1; 2 – KOS- 1; 3 – UD-1; 4 – KNC-1, KNC-4; 5 – MRA-1, 6 – MRA-2, 7 – MRA-3, 8 – MRA-4).

65 BÓNOVÁ et al. / Turkish J Earth Sci glauconite-sandstone facies, whereas the upper part is Proč Fm. is commonly regarded as a part of the Pieniny usually formed by the claystone facies. The total thickness Klippen Belt (e.g., Nemčok, 1990; Lexa et al., 2000). of the formation is reaching 1500–2500 m. The Inner Rača Latter research in the this area proved the facies transition Unit superficially covers a considerably larger area. It has (Jasenovce Mb.) between the Proč and Strihovce fms more variegated facies content than the Outer Rača Unit. and so both formations constitute an integral part of the It is built of the following formations: Kurimka Fm. (sensu Krynica Unit (Potfaj in Žec et al., 2006). The Strihovce Fm. Samuel, 1990); Beloveža, Zlín, and Malcov fms (Kováčik (Early Eocene – Late Eocene) dominates in the eastern et al., 2011, 2012). The underlier of the Kurimka Fm. part of Flysch Belt (Žec et al., 2006; Kováčik et al., 2012) (Late Cretaceous – Early Eocene) is not known, towards and represents several 100-m-thick bed successions the overlier it gradually evolves into the Beloveža Fm. of quartzose-greywacke (Strihovce) sandstones with The formation is divided into flysch and sandstone facies. intercalations of conglomerates. A significant facies is The Beloveža Fm. (Palaeocene – Middle Eocene) crops represented by the polymictic conglomerates with exotic out in the frontal parts of particular slices (or in cores of pebbles (Marschalko et al., 1976; Mišík et al., 1991a): anticlinal structures) of the Inner Rača Unit. The lower granite, orthogneiss, micaschist, metalydite, migmatite, part of the formation is formed by the Mrázovce Member, quartz porphyry, rhyolite, and basic volcanics. Arkose, whereas the upper part is formed by thin-bedded flysch arkosic quartzite, Triassic limestones containing ostracods with the intercalations of variegated claystones. The and foraminifers, Jurassic siliceous limestones with thickness of the Beloveža Fm. commonly reaches 200–250 chert, radiolarian siliceous limestones, dark flecked marl m, with maximum up to 2000 m (Nemčok et al., 1990). The limestones (“fleckenmergel”), Dogger-Malm biomicrites, lowermost part of the Beloveža Fm. – Mrázovce Member Kimmeridgian-Tithonian shallow-water and pelagic (sensu Kováčik et al., 2012) has a character of the upward- limestones, Late Jurassic-Early Cretaceous limestones with fining and upward-thinning flysch succession (channel- calpionels, and Cretaceous, Palaeocene to Middle Eocene levee complex) with palaeoflow direction prevailingly limestones and sandstones with foraminifers were also from NW to SE (Kováčik and Bóna, 2005). In the group of identified (Mišík et al., 1991a). Significant for the Strihovce crystalline exotic pebbles within the Mrázovce Mb. were conglomerates are red orthogneisses (Marschalko et al., found muscovite-biotite quartzite, quartzitic paragneiss, 1976). In the Eocene deposits of an equivalent formation quartzitic micaschist, granodiorite, and ultrabasic? rock. (the Piwniczna Sandstone Member of the Magura Formation Limestones, sandstone, and chert were also described and Tylicz/Krynica facies, Olszewska and Oszczypko, (Kováčik et al., 2012). The overlier of the Beloveža 2010) in Poland were found granitoids, gneisses, mica Fm. is formed by the Zlín Fm. (Middle Eocene – Early schists, phyllites, quartzites, and a small amount of basic Oligocene). The formation is composed of several facies volcanic rocks and Mesozoic carbonates (Oszczypko, 1975; (or lower lithostratigraphic units): Makovica sandstones Oszczypko et al., 2006, 2016). Analyses of heavy mineral with local layers of conglomerate, glauconite-sandstone suites from the Strihovce Fm. showed garnet dominance facies, coarse-grained sandstones and conglomerates, over zircon, rutile, tourmaline, and staurolite (Ďurkovič, claystone facies, and dark-grey and olive-green calcareous 1960; Starobová, 1962; Bónová et al., 2010). High Cr- claystones with quartzose-carbonate and glauconitic spinel content was also noted (Starobová, 1962; Winkler sandstones. The transition into the overlying Malcov and Ślączka, 1992; Bónová et al., 2017). Maťašovský (1999) Formation (Late Eocene – ?Late Oligocene) is gradual at described the garnet, ilmenite, rutile, zircon, leucoxene, numerous places and a common occurrence of the Malcov epidote, tourmaline, apatite, pyroxene, and gold. The sandy and Zlín lithotypes is expressed by the defining of the Zlín- claystones are developed in the overlier of these polymictic Malcov facies (calcareous claystones, quartzose-carbonate, conglomerates. The flysch facies is locally presented with and glauconitic sandstones). intercalations of variegated claystones. The Malcov Fm. The Bystrica Unit is overthrusted on the Inner Rača (Late Eocene – ?Late Oligocene) is the youngest formation Unit in the north-eastern side and in the south it is of the KU in the region. For the KU, sedimentary gravity in tectonic contact with the Krynica Unit. The oldest flows brought clastic material mostly from S, SE, and E to lithostratigraphic unit is the Beloveža Fm. (Palaeocene – the N, NW, and W (longitudinal filling, Koráb et al., 1962). Middle Eocene) consisting of the sandstone facies (locally Several data point to the directions from SW to NE. It was with conglomerates) and the thin-bedded flysch. The Zlín supposed that the lateral filling longitudinally turned to Fm. (Middle Eocene – Late Eocene) is formed prevailingly the axis of the basin (l. c.). by the sandstone facies and claystone facies. During the Late Cretaceous to Palaeogene the Magura The Krynica Unit is the southernmost tectono- Basin was supplied with clastic material from source areas lithofacies unit of the Magura Nappe. It consists of the situated on the northern and southern margins of the Proč, Čergov, Strihovce, and Malcov formations. The basin.

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The northern source area is traditionally associated of the Magura Basin (l. c.). Marschalko et al. (1976) with the Silesian Ridge/Cordillera (e.g., Ksiązkiewicz, suggested the consuming of the South-Magura Cordillera 1962; Eliaš, 1963; Krystek, 1965; Soták, 1986; 1990; 1992; during the Oligocene. According to Potfaj (1998), this Grzebyk and Leszczyński, 2006), but other sources like cordillera existed only until the Middle Eocene. Based the Bohemian Massif (Nemčok et al., 2000) and European on the study of exotic crystalline pebbles, Oszczypko et Platform (Golonka et al., 2000, 2003; Golanka, 2011) al. (2006), Salata and Oszczypko (2010), and Olszevska were also proposed. The Silesian Ridge/Cordillera was an and Oszczypko (2010) devised the Eocene exhumation elevated area, consisting of the pre-Albian formations of of the Magura basement in the KU. The siliciclastic the Magura substratum and tectonically annexed parts material could also be supplied from a SE source area of the Brunovistulicum (Soták, 1990, 1992), or it was (Dacia and Tisza Mega-Units) and carbonate material originally part of the North European Platform (Golonka from the ALCAPA Mega-Unit: Central Carpathian et al., 2014). It is known only from exotics and olistoliths Block and Pieniny Klippen Belt (l. c.). This interpretation occurring within the various units of the Outer Western of carbonate source could be excluded because of the Carpathians (l. c.). The Silesian Ridge was uplifted different biofacies of the Mesozoic sequences (Mišík et in the Late Cretaceous to Palaeocene (Poprawa and al., 1991a). Palaeogeographic reconstructions based on Malata, 2006), to Middle Eocene (Kováč et al., 2016) or the heavy mineral composition of the Eocene-Oligocene up to the Oligocene (Ksiązkiewicz, 1962; Golonka et al., deposits and Cr-spinel geochemistry supported by the 2006). Golonka et al. (2006) and Waśkowska et al. (2009) palaeoflow data suggest that during the Eocene to Lower suggested an existence additional intrabasinal ridge, the Oligocene the source area for the eastern part of the Fore-Magura Ridge, which supplied the Magura basin Magura Basin was located in the Fore-Marmarosh suture during the Palaeocene from the North. According to Mišík zone (Eastern Carpathians; Bónová et al., 2017). Late et al. (1991a) the Silesian Cordillera had no equivalent in Eocene to Late? Oligocene deposits mainly in the RU the eastern-Slovakian zone of the Flysch Belt. could be derived from the Marmarosh Massif and also The southern source area is not still unambiguously the Fore-Marmarosh Suture. For the KU, a significant determined. Leško (1960) and Leško and Samuel (1968) contribution of detrital material from medium- to high- proposed the Marmarosh Cordillera (partially identified grade metamorphic complexes of the Villáni-Bihor and with the present development of the Marmarosh Massif), Békés-Codru zones (crystalline basement of the Tisza which detached the Magura and Klippen Belt spaces Mega-Unit) was proposed by Bónová et al. (2016). Part of until the Late Lutetian in the east. On the other hand, the clastic material could be redeposited from older flysch the Marmarosh Ridge is considered an extension of the formations (l. c.). Silesian Ridge (Bąk and Wolska, 2005) and could feed the Magura Basin from the north-eastern side (e.g., Oszczypko 3. Sampling and methods et al., 2005, 2015). The presence of the intrabasinal Quantitative exotic pebble analysis (130 pebbles with Marmarosh Ridge between the Magura and Dukla basins parameters up to 11 cm) was performed for several was also suggested (Leszczyński and Malata, 2002; Ślączka localities within the Mrázovce Mb. deposits. The pebble et al., 2006; Gągała et al., 2012). It uplifted during the material was obtained from an exposure in the Mrázovce Late Eocene and drowned in the Early Oligocene due to stream (GPS: N 49°06.446, E 21°39.385) and from debris tectonic loading (Gągała et al., 2012). Koráb and Ďurkovič of the conglomerate occurrences (GPS: N 49°06.727, (1973, 1978) demonstrated the existence of a mutual E 21°39.611, Figures 1a and 1b). The thin sections were sedimentary basin for the Magura and Dukla units during prepared from 25 samples and were examined under the Middle Cretaceous to Early Oligocene in eastern a polarising microscope. Published data were used for the Slovakia, i.e. these units were sedimented in a basin Strihovce Fm. (Oszczypko, 1975; Marschalko et al., 1976; that was not divided by a cordillera. Ślączka and Wieser Mišík et al., 1991a). Sandstone samples were selected for (1962) and Ślączka (1963) proposed small islands of the optical heavy mineral analysis covering the Strihovce Fm. Marmarosh and Rachov massifs situated between the from the Krynica unit (KU) and the Mrázovce Mb. from Dukla and Silesian (northern) subbasins. Nemčok et al. the Rača unit (RU). (1968), Nemčok (1970), and Samuel (1973) also envisaged For the KU, heavy minerals were separated from the an exotic cordillera that had been fed to the Magura Basin sandstone-conglomerate facies (Strihovce Sandstones s. from the south. For the KU (Strihovce Fm.), Marschalko s.) of the Kamenica n/Cirochou and Košarovce localities et al. (1976) and Mišík et al. (1991a) devised the South- (KNC-1, KNC-4, and KOS-1 samples), from the flysch Magura Cordillera (Magura Cordillera sensu Rakús et al., facies of the Giraltovce locality (GIR-1 sample), and from 1990). This cordillera was active predominantly during the matrix of polymictic conglomerates of the Udavské the Eocene and was constituted from the substratum locality (UD-1 sample).

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For the RU, heavy minerals were recovered from the 4. Results MRA-1, MRA-2, MRA-3, and MRA-4 samples of the 4.1. Exotic pebble analysis Mrázovce locality (Figure 1b). Krynica Unit. Composition of pebbles considered in The weight of the samples was about 3–5 kg. To the discussion was excerpted from the published data separate the heavy minerals, the samples were crushed, (Oszczypko, 1975; Marschalko et al., 1976; Mišík et al., sieved, and gently washed by water across a Wilfley 1991a). vibrating table. In this study, the total heavy mineral Rača Unit. About 23% of the pebbles analysed are concentrates were obtained from the grain-size fraction represented by phyllite, garnet micaschist, and gneisses of 0.01–0.63 mm through the standard separation method (Figures 2a and 2c), 6% of them are formed by tourmaline- using tribromomethane with a specific gravity of 2.89 g/ 3 bearing pale granite (Figure 2b), and 3% of the exotics cm . Approximately 350 translucent heavy minerals were belong to cataclastic granite. About 38% of pebbles counted in randomly selected traverses for each sample. appertain to subarkose, quartz arenite, and quartzite, Detrital minerals (garnets, tourmalines, and zircons) following organogenic limestone, limestone (10%), were embedded in epoxy resin and polished. Minerals and dark siliceous rocks (19%). Some limestone pebbles were analysed in polished thin sections using an electron show signs of a syngenetic splitting connected with the microanalyser (CAMECA SX 100, State Geological matrix penetrating them. Rounded quartz is the most Institute of Dionýz Štúr, Bratislava, Slovak Republic) with abundant (it is not counted in the statistics considering its the WDS method at accelerating voltages of 15 kV, beam high concentration). current of 20 nA, and electron beam diameter of 5 µm. To Petrographic characteristics of pebbles. Phyllite is measure concentrations of various elements the following fine-grained rock composed mainly of undulose quartz, natural and synthetic standards were used: orthoclase (Si biotite, white mica, and plagioclase feldspar, rarely Kα), TiO (Ti Kα), Al O (Al Kα), Cr (Cr Kα), fayalite (Fe 2 2 3 graphite. Secondary minerals are represented by calcite Kα), rhodonite (Mn Kα), forsterite (Mg Kα), wollastonite and hematite (after opaque minerals). In some samples (Ca Kα), NiO (Ni Kα), willemite (Zn Kα), and V O (V Kα). 2 5 the biotite is baueritised or intensively chloritised. The crystallochemical formula of garnet was normalised to 12 oxygens and conversion of iron valence (Fe3+ and Garnet micaschist is formed by undulose quartz and Fe2+) according to ideal stoichiometry. Analysed points for feldspar containing the anhedral crystals of garnet. The tourmaline were located in the centre, on the core-rim and subhedral garnet porphyroblasts show signs of local on the rim of the grains. Tourmaline structural formula chloritisation. They are often surrounded by quartz and was calculated on the basis of 31 oxygens, (OH + F) = 4 white mica, more sporadically by chloritised biotite. a.p.f.u., B = 3 a.p.f.u. Cathodoluminescence was used for Garnet porphyroblasts represent grossular-almandine the observation of the zircon zoning. It was carried out with a spessartine component, the content of which with the same instrument at an accelerating voltage of 8 kV decreases slightly toward the rim (Alm76-78Grs12-14Prp7- –3 and beam current of 1 × 10 nA. Silicates in pebble exotics 8Sps1-5). Zircon, tourmaline, and opaque minerals are in were studied by electron microprobe JEOL JXA 8530FE accessory amounts. Subhedral zoned dravitic tourmaline at the Earth Sciences Institute in Banská Bystrica (Slovak [Mg/(Mg + Fe) = 0.6-0.72] is subrounded by mica and Republic) under the following conditions: accelerating quartz. Quartz and chlorite penetrate the tourmaline grain voltage 15 kV, probe current 20 nA, beam diameter 2–5 and form its microboundinage, signalising the brittle µm, ZAF correction, counting time 10 s on peak, 5 s on deformation behaviour of minerals (Figure 2d). Gneiss background. Used standards, X-ray lines, and D.L. (in shows usually a banded texture. The first type of gneisses ppm) are: Ca(Kα, 25) – diopside, K (Kα, 44) – orthoclase, consists of the K-feldspar and plagioclase, which form the F (Kα, 167) – fluorite, Na (Kα, 43) – albite, Mg (Kα, 41) porphyroblasts in the quartz-muscovite matrix. Zircon, – olivine, Al (Kα, 42) – albite, Si (Kα, 63) – quartz, Fe staurolite, and kyanite (?) rarely occur. In the second type of gneisses, the porphyroblasts are represented by a (Kα, 52) – hematite, Cr (Kα, 113) – Cr2O3, Mn (Kα, 59) destroyed (retrograde) garnet (Figure 2a) coupled with – rhodonite, V (Kα, 117) – ScVO4, Ti (Kα, 130) – rutile, Cl (Kα, 12) – tugtupite. Their structural formulas were K-feldspar, chloritised biotite, and quartz in the quartz- calculated as previously described. muscovite matrix. The chemical composition of garnet Selected heavy minerals were analysed via scanning corresponds to almandine with variable content of electron microscopy (SEM) using a TESCAN VEGA-3 grossular and spessartine molecules (Alm73-79Prp5-8Grs9-

XMU (operating at 20 kV) equipped with an EDX energy 12Sps3-10). The rock foliation is surmounted by graphite. dispersive spectrometer for their surface characterisation Ore minerals and zircon rarely occur. The porphyroblasts (Department of Condensed Matter Physics, Pavol Jozef in the third type of gneisses are composed of the sigmoidal

Šafárik University in Košice, Slovak Republic). The mineral garnets enclosed in TiO2 polymorphs, zircon, and apatite samples were fixed on a carbon sticker and covered by Au. and also of the sericitised K-feldspars. The geochemistry

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Figure 2. Microphotographs in plane polarised light (a, b) and backscattered electron images (c–f) of exotic pebbles from the Mrázovce Mb. deposits: a) retrograde garnet coupled with K-feldspar in gneiss pebble; b) pleochroic tourmaline in granite pebble; c) euhedral (prograde) garnets enclosed in plagioclase in gneiss pebble; d) tourmaline from micaschist pebble with fractures filled by quartz and chlorite; e, f) c in detail. of garnet indicates uniform composition as in a previous of quartz, K-feldspar, and plagioclase. Detrital zircon, type (Alm78-82Prp4-8Grs8-11Sps2-7). A groundmass consists muscovite, chloritised biotite, and epidote are present in mainly of muscovite with biotite. Adjacent to the garnets accessory amounts. The matrix contains opaque minerals, there is a slightly higher proportion of quartz and feldspar probably iron oxides. The quartz is the main component of than in the micaceous part of the groundmass. This type the quartz arenite. The altered feldspars, platy white mica, of gneisses is characterised by the highest quartz content. detrital zircon, tourmaline, and hematite (after opaque Euhedral small garnets enclosed in plagioclase are minerals) are scarce. This rock is cemented by calcite characteristic for the fourth type of gneisses (Figures 2c, cement. Another type of quartz arenite shows the corrosive 2e, and 2f). EMP analyses revealed their zoned character. structure; the original shape of quartz grains is intensively Garnets show grossular-almandine composition with destroyed by a corrosive influence of the hematite cement. an increase of the pyrope component at the expense of Quartz is the dominant grain type in quartzite. Biotite the grossular toward the rim, signalising the prograde and muscovite slices, sericitised and partially deformed metamorphism (Alm63-68Prp5-9Grs20-27Sps1-5). Biotite, feldspar with kink bands, zircon, rutile, and apatite are an muscovite, quartz, zircon, rutile, and ore minerals are also unsubstantial. Some quartzite pebbles are cut by calcite present. Cataclastic granite consists mainly of K-feldspar, veins. The recrystallized quartz and bands of graphite are plagioclase, undulose and partially recrystallised quartz, the main component of graphitic quartzite. Limestone rare muscovite, and pseudomorphosis after pyrite. Some pebbles are represented either by clustered ones (calcite quartz crystals seem to be distinctly elongated. The mass with unsharp restricted clusters of calcite mud) fractures in feldspars are filled by quartz. Granite consists or organogenic limestones with dispersed microfossils of quartz, orthoclase, microcline showing evident cross- (foraminifers). hatched twinning, plagioclase with lamellar twining, and 4.2. Heavy minerals tourmaline showing very distinct pleochroism (Figure 2b). Heavy mineral assemblages (HMAs) of the Strihovce Zoned tourmaline shows schorlitic-dravitic composition Fm. (KU) consist of high proportions of garnet, zircon, (molar XMg = [Mg/(Mg + Fe)] varies from 0.45 to 0.56). rutile, and apatite. Subordinate amounts were obtained for The alkali feldspar is present in much higher proportions tourmaline, epidote, staurolite, and Cr-spinel. Pyroxene, than the plagioclase. The zircon and white mica are amphibole, glauconite, kyanite, monazite, and titanite accessory minerals. Subarkose is composed mainly rarely occur. The HMA of the Mrázovce Mb. (RU) is

69 BÓNOVÁ et al. / Turkish J Earth Sci comparable to that of the KU (Figure 3) but certain locally occurs (Figure 4e). Zircon is mildly rounded or differences are a mildly higher tourmaline concentration euhedral and usually unweathered (Figure 4f). than in the Strihovce Fm. and the occurrence of barite. Rača Unit. Contrary to the Strihovce Fm. deposits, 4.2.1. Corrosion features detrital garnets from the Mrázovce Mb. show deeply etched Surface textures of detrital minerals usually range to faceted grain surfaces. Weathering intensity of garnets is from incipient corrosion to deep etching, reflecting a diverse (Figures 4g and 4h); grains with large-scale facets progressively increasing degree of weathering. Some broadly prevail (Figure 4g). Stable minerals such as zircon, ultrastable to stable grains are unweathered. Surface tourmaline, rutile, and apatite also show signs of corrosion. textures of the selected minerals are documented in Figure 4. Zircon occasionally displays corrosion, preferentially Krynica Unit. According to classification of Andò metamictic grains. Some have euhedral shape (Figure 4i). et al. (2012), a few detrital garnets represent almost Apatite and tourmaline usually show subhedral outlines unweathered euhedral grains (Figure 4a), but nevertheless and incipient corrosion (Figure 4j). Other tourmalines are the bulk of isometric grains are slightly rounded. Some completely transformed by corrosion to rounded grains garnets show a slight to advanced degree of corrosion. with significant etch pits (Figure 4k). Subrounded to The textures caused by both weathering/dissolution and rounded (recycled) rutile grains reveal an initial to slight abrasion are observed on the same grain (Figure 4b). The degree of corrosion (Figure 4l). mass of grains commonly show corroded outlines and 4.2.2. Heavy mineral ratios large-scale facets (Figure 4c), and less frequently etch pits The relative abundance of heavy minerals is reflected by (Figure 4d). Among stable minerals, tourmaline is usually the mineral indexes of garnet/zircon (GZi), chromian angular and unweathered, sometimes subrounded with an spinel/zircon (CZi), and apatite/tourmaline (ATi) initial to slight degree of corrosion, while corroded rutile (Morton and Hallsworth, 1994, 1999; Morton et al., 2005).

[%] 100

90 Brt Ttn 80 Amp Mnz 70 Px Spl 60 Ky Ep 50 St Tur 40 Rt Zrn 30 Ap Glt 20 Grt 10

0 KNC-1 KOS-1 UD-1 GIR-1 MRA-1 MRA-2 MRA-3 MRA-4 Figure 3. Heavy minerals in samples (%) from deposits of the formations investigated. Grt – Garnet, Glt – glauconite, Ap – apatite, Zrn – zircon, Rt – rutile, Tur – tourmaline, Sta – staurolite, Ep – epidote, Ky – kyanite, Spl – spinel, Px – pyroxene, Mnz – monazite, Amp – amphibole, Ttn – titanite, Brt – barite.

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a b c d

e f g h

i j k l

Figure 4. Scanning electron microscope images of detrital minerals point to their corrosion features from the Strihovce Fm. (a–f) and Mrázovce Mb. (g–l) deposits, respectively. For detailed description see the text.

The garnet versus zircon ratio, which is used to detect suites of first-cycle origin (Morton and Hallsworth, 1994). increasing chemical modification with sediment burial, Its rather high value indicates that a positive proportion ranges from 58 to 75 for the Strihovce Fm. and from 72 to of ophiolite detritus was chiefly supplied for the KU. 79 for the Mrázovce Mb. deposits. The apatite/tourmaline On the other hand, the CZi values are negligible in the index, which is best suited for unravelling chemical Mrázovce Mb. deposits. The ZTR index (percentage of the alteration at the source and/or transport, is consistently combined zircon, tourmaline, and rutile grains among the high in all samples from the Strihovce Fm. (70–91), while transparent, nonmicaceous, detrital heavy minerals, sensu lower values (40–51) are common for the Mrázovce Mb. Hubert, 1962), which reflects the sediment maturity, is deposits. Interestingly, apatite is completely lacking in within the range of 34%–36% (sporadically 46%) for the the MRA-4 sample. The chromian-spinel/zircon index, Strihovce Fm. and from 28% to 41% for the Mrázovce Mb. which varies from 3.4 to 5 in the Strihovce Fm., provides 4.2.3. Heavy mineral geochemistry a good reflection of source area characteristics because Heavy mineral analyses were performed aiming at these minerals are comparatively immune to alteration identifying possible differences in heavy mineral during the sedimentary cycle. This index could be used to compositions that can be accounted to the sediment directly match sediments with source materials, even for provenance of each formation. This study is focused on

71 BÓNOVÁ et al. / Turkish J Earth Sci garnet (Table 1) and tourmaline (Table 2). These mineral from inclusions, or colourless with dark dusty inclusions. groups show some chemical variations. Results are shown The composition of garnets studied is illustrated in the in Figure 5. ternary classification diagram of Morton et al. (2004) Garnet. Detrital garnets from the KU form either using almandine + spessartine, pyrope, and grossular irregular sharp fragments or isometric subrounded grains. as poles and the discrimination fields A, B I, B II, and C Contrary to it, garnets from the RU are predominantly (Figure 5a). represented by subangular and subrounded fragments with Krynica Unit. Garnets from the sandstone-conglomerate apparent corrosion-induced marks (above-mentioned). facies (KNC-1, KNC-4, KOS-1 samples) are represented

Garnets in both units are pink and pale orange, usually free by the pyrope-almandines (Alm73-83Prp10-20Grs2-4Sps3-7),

Table 1. Representative microprobe analyses of detrital garnets from the Strihovce Fm. (KU) and the Mrázovce Mb. (RU) deposits. Oxides are in wt.%.

Mineral Garnet

Unit Krynica Unit Rača Unit

Sample UD-1 GIR-1 KNC-1 KOS-1 MRA-1 MRA-2 MRA-3

Point c r c r c r c r c r c r c r

SiO2 38.92 38.39 36.70 36.71 36.17 36.51 36.81 36.79 37.16 37.89 38.06 37.54 37.40 38.40

TiO2 0.51 0.10 0.00 0.00 0.00 0.15 0.01 0.01 0.17 0.05 0.02 0.00 0.07 0.11

Al2O3 21.38 21.40 20.86 21.18 21.37 21.13 20.58 21.15 20.62 20.67 20.97 20.82 21.07 21.05

Cr2O3 0.00 0.00 0.03 0.03 0.02 0.00 0.02 0.04 0.00 0.00 0.01 0.01 0.00 0.01

Fe2O3* 0.00 0.00 2.48 1.58 2.62 2.13 2.71 1.52 0.00 0.00 0.00 0.00 0.00 0.00 FeO 26.34 25.57 27.09 27.54 30.71 13.95 30.11 30.95 18.46 19.48 31.49 31.62 25.54 23.49 MnO 0.22 0.19 8.47 8.36 7.76 18.88 5.74 5.72 17.34 13.34 2.69 3.48 5.32 2.06 MgO 6.67 5.82 3.49 3.28 1.89 0.19 3.40 2.96 1.10 1.80 5.27 4.33 1.02 0.77 CaO 5.59 7.38 1.55 1.60 1.02 8.10 1.59 1.54 5.14 6.68 1.01 1.02 9.39 14.21 Total 99.62 98.86 100.7 100.3 101.5 101.1 101.0 100.7 100.0 99.91 99.52 98.82 99.80 100.1 Si 3.033 3.016 2.940 2.949 2.908 2.928 2.946 2.952 3.007 3.039 3.034 3.033 3.000 3.040 Ti 0.030 0.006 0.000 0.000 0.000 0.009 0.001 0.000 0.010 0.003 0.001 0.000 0.004 0.007 Al 1.964 1.982 1.969 2.005 2.025 1.997 1.942 2.000 1.967 1.955 1.970 1.982 1.992 1.964 Cr 0.000 0.000 0.002 0.002 0.001 0.000 0.001 0.003 0.000 0.000 0.001 0.001 0.000 0.000 Fe3+ 0.000 0.000 0.150 0.096 0.159 0.129 0.163 0.092 0.000 0.000 0.000 0.000 0.000 0.000 Fe2+ 1.717 1.680 1.815 1.849 2.065 0.936 2.015 2.077 1.249 1.307 2.100 2.136 1.713 1.555 Mn 0.014 0.012 0.575 0.569 0.529 1.282 0.389 0.389 1.189 0.907 0.182 0.238 0.362 0.138 Mg 0.775 0.682 0.417 0.392 0.227 0.023 0.406 0.355 0.133 0.215 0.626 0.522 0.122 0.091 Ca 0.467 0.622 0.133 0.138 0.088 0.696 0.136 0.133 0.446 0.574 0.086 0.088 0.807 1.205 Total 8 8 8 8 8 8 8 8 8 8 8 8 8 8 Alm 57.75 56.07 61.73 62.72 71.01 31.86 68.39 70.34 41.40 43.53 70.13 71.58 57.04 52.01 Prp 26.07 22.76 14.19 13.31 7.79 0.78 13.78 12.01 4.42 7.16 20.92 17.49 4.05 3.05 Grs 15.46 20.69 4.20 4.46 2.80 22.17 4.26 4.29 14.70 19.09 2.87 2.96 26.82 40.17 Sps 0.48 0.42 19.55 19.29 18.18 43.66 13.21 13.16 39.41 30.19 6.08 7.98 12.04 4.63 Uv 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.01 0.00 0.00 0.00 0.00 0.00 0.01 Adr 0.00 0.00 0.32 0.21 0.22 1.43 0.36 0.20 0.00 0.00 0.00 0.00 0.00 0.00 Ca-Ti Grt 0.24 0.06 0.00 0.00 0.00 0.10 0.00 0.00 0.08 0.03 0.00 0.00 0.05 0.14

Fe2O3* – calculated; c – core, r – rim.

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Table 2. Representative microprobe analyses of detrital tourmalines from the Strihovce Fm. (KU) and the Mrázovce Mb. (RU) deposits. Oxides are in wt.%.

Mineral Tourmaline

Unit Krynica Unit Rača Unit

Sample UD-1 GIR-1 KNC-1 KOS-1 MRA-1 MRA-2 MRA-3 MRA-4

Point c r c r c r c c/r r c c/r r c r c r c c/r r

SiO2 37.21 37.60 36.55 37.34 36.95 36.98 37.12 36.72 36.57 36.83 36.83 36.56 35.10 36.58 36.84 36.92 37.14 36.79 37.01

TiO2 0.77 0.67 1.04 0.71 0.43 1.08 2.64 0.53 0.88 0.81 0.28 0.65 0.11 0.85 0.42 0.59 0.29 1.18 0.75

B2O3* 10.63 10.79 10.66 10.82 10.80 10.59 10.78 10.45 10.59 10.65 10.52 10.49 10.23 10.48 10.57 10.51 10.56 10.51 10.64

Al2O3 30.98 32.13 32.73 33.77 34.91 30.50 29.04 30.91 32.21 29.64 31.31 31.05 33.44 30.51 31.25 30.57 31.07 29.98 31.38

Cr2O3 0.00 0.09 0.19 0.06 0.05 0.05 0.26 0.03 0.16 0.06 0.05 0.08 0.04 0.04 0.05 0.07 0.00 0.06 0.00 MgO 6.67 8.31 7.61 7.89 5.63 6.86 11.72 5.14 6.19 10.47 6.34 6.07 0.57 6.44 5.81 5.79 5.59 5.53 6.01 CaO 0.30 0.40 0.93 0.59 0.54 0.51 2.56 0.10 0.48 2.63 0.07 0.55 0.17 0.62 0.08 0.09 0.10 0.20 0.36 MnO 0.00 0.00 0.05 0.05 0.04 0.02 0.00 0.02 0.00 0.02 0.03 0.01 0.09 0.04 0.07 0.05 0.03 0.06 0.01

FeOtot 8.23 4.65 4.04 3.06 6.25 7.89 0.53 10.10 7.15 3.52 8.00 8.46 14.37 8.09 9.59 9.51 9.97 10.43 9.06

Na2O 2.44 2.42 1.79 1.96 1.73 2.32 1.46 2.24 2.03 1.43 2.42 2.03 1.57 2.20 2.68 2.66 2.54 2.51 2.46

K2O 0.02 0.02 0.06 0.04 0.03 0.03 0.05 0.01 0.01 0.02 0.02 0.01 0.03 0.01 0.01 0.01 0.00 0.01 0.01 NiO 0.00 0.00 0.00 0.02 0.00 0.00 0.00 0.02 0.01 0.02 0.16 0.03 0.00 0.00 0.01 0.00 0.01 0.01 0.00 F 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.08 0.00 0.00 0.05 0.00 0.00 0.00 0.00 0.00 Cl 0.01 0.01 0.02 0.01 0.01 0.00 0.02 0.01 0.02 0.01 0.00 0.00 0.00 0.00 0.00 0.01 0.00 0.01 0.01

H2O* 3.66 3.71 3.67 3.72 3.72 3.64 3.71 3.60 3.64 3.67 3.62 3.61 3.52 3.61 3.64 3.62 3.64 3.62 3.66 O=F –0.01 –0.01 –0.01 –0.01 –0.01 –0.01 –0.01 –0.01 –0.01 0.00 0.03 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 Total 100.9 100.8 99.33 100.1 101.1 100.5 99.90 99.88 99.94 99.78 99.77 99.61 99.24 99.51 101.02 100.39 100.94 100.90 101.36 Si 6.083 6.054 5.958 6.000 5.946 6.071 5.985 6.106 6.002 6.010 6.078 6.060 5.963 6.065 6.056 6.105 6.110 6.085 6.047 AlT 0.000 0.000 0.042 0.000 0.054 0.000 0.015 0.000 0.000 0.000 0.000 0.000 0.037 0.000 0.000 0.000 0.000 0.000 0.000

T tot. 6.083 6.054 6.000 6.000 6.000 6.071 6.000 6.106 6.002 6.010 6.078 6.060 6.000 6.065 6.056 6.105 6.110 6.085 6.047 B 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 Cr 0.001 0.011 0.025 0.008 0.006 0.007 0.033 0.004 0.021 0.007 0.007 0.011 0.005 0.005 0.006 0.010 0.000 0.008 0.000 AlY+Z 5.969 6.099 6.247 6.396 6.568 5.902 5.503 6.058 6.229 5.700 6.090 6.066 6.660 5.961 6.055 5.958 6.025 5.845 6.044 Ti 0.095 0.081 0.127 0.086 0.052 0.133 0.320 0.066 0.108 0.099 0.035 0.082 0.014 0.106 0.052 0.073 0.036 0.147 0.092 Fe 1.125 0.626 0.550 0.411 0.841 1.083 0.072 1.405 0.981 0.481 1.104 1.173 2.042 1.122 1.319 1.316 1.372 1.443 1.238 Mn 0.000 0.000 0.007 0.007 0.005 0.003 0.000 0.003 0.000 0.003 0.005 0.001 0.013 0.005 0.009 0.007 0.004 0.009 0.002 Mg 1.625 1.994 1.850 1.890 1.350 1.679 2.816 1.275 1.514 2.547 1.561 1.500 0.145 1.591 1.423 1.427 1.371 1.363 1.463 Ni 0.000 0.000 0.000 0.002 0.000 0.001 0.000 0.003 0.001 0.002 0.021 0.004 0.000 0.000 0.001 0.000 0.001 0.001 0.001

Y+Ztot. 8.814 8.810 8.806 8.800 8.822 8.806 8.744 8.813 8.855 8.839 8.821 8.836 8.879 8.791 8.865 8.790 8.809 8.816 8.839 Ca 0.052 0.070 0.163 0.102 0.093 0.090 0.442 0.017 0.085 0.459 0.012 0.097 0.031 0.110 0.015 0.016 0.018 0.036 0.062 Na 0.772 0.754 0.567 0.611 0.539 0.738 0.457 0.723 0.646 0.454 0.775 0.651 0.517 0.707 0.855 0.853 0.810 0.806 0.779 K 0.005 0.004 0.012 0.008 0.007 0.005 0.011 0.002 0.002 0.005 0.003 0.003 0.006 0.002 0.001 0.002 0.001 0.002 0.002

X tot. 0.830 0.828 0.741 0.721 0.639 0.834 0.910 0.742 0.733 0.918 0.790 0.751 0.554 0.819 0.871 0.871 0.829 0.843 0.844

Xvac. 0.170 0.172 0.259 0.279 0.361 0.166 0.090 0.258 0.267 0.082 0.210 0.249 0.446 0.181 0.129 0.129 0.171 0.157 0.156 F 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.042 0.000 0.000 0.026 0.000 0.000 0.000 0.000 0.000 Cl 0.003 0.001 0.004 0.002 0.002 0.000 0.006 0.002 0.007 0.001 0.000 0.000 0.000 0.000 0.001 0.002 0.000 0.003 0.001 Mg# 0.59 0.76 0.77 0.82 0.62 0.61 0.98 0.48 0.61 0.84 0.59 0.56 0.07 0.59 0.52 0.52 0.50 0.49 0.54

B2O3*, H2O* – calculated; vac. – vacancy; c – core, c/r – core/rim, r – rim; Mg# – Mg/(Mg+Fe).

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XMg

Strihovce Fm. Mrázovce Mb. exotic pebbles: mica schist, gneiss a

A

ype T Type C

ype B I T Type B II

XFe+Mn XCa Al Elbaite

b 1 Strihovce Fm. Mrázovce Mb. exotic pebbles: mica schist granite Alkali-free dravite

4 7 Schorl 2 5 Dravite Buergerite

3 6 8

Uvite

Al50Fe(tot)50 Al50Mg50 Figure 5. a) Composition of detrital garnets from the siliciclastics studied and exotic pebbles in a Fe + Mn-Mg-Ca ternary diagram (Morton et al., 2004): type A – Grt from granulites; type BI – Grt from intermediate to acid igneous rocks; type B II – Grt from metasedimentary rocks of amphibolite facies; type C – Grt from metabasic rocks. b) Al-Fe-Mg diagram for tourmalines (Henry and Guidotti, 1985). (1) Li-rich granites; (2) Li-poor granites and aplites; (3, 6) Fe3+-rich quartz-tourmaline rocks; (4) metapelites and metapsammites coexisting with Al-rich phases; (5) metapelites and metapsammites not coexisting with Al-rich phases; (7) low-Ca metaultramafic rocks, Cr- and V- rich metasedimentary rocks; (8) metacarbonates and metapyroxenites.

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grossular-pyrope-almandines (Alm55Prp28Grs15Sps1), the sandstone-conglomerate facies (KNC-1, KNC-4, and almandines (87 mol% Alm), and unzoned grossular- KOS-1 samples) could be divided into three categories: almandines (Alm78Grs11Prp6Sps4Adr1). Zoned garnets, in zoned grains with an inherited core (Figures 6a and 6b), which almost all end-member species vary, specifically a developed inner rim, and overgrowth marginal zone; from (Alm71Sps18Prp8Grs3) to (Alm32Prp1Grs22Sps44), or zoned grains with no inherited core; and unzoned grains. from (Alm48Prp4Grs18Sps29) to (Alm68Prp11Grs17Sps3), are Zoned tourmalines display a shift from schorlitic-dravitic also found. Quartz, tourmaline, and biotite represent the inherited core to overgrowth showing dravitic composition inclusions. For the matrix of polymictic conglomerates in the rim (sensu Henry et al., 2011). Some inherited cores

(UD-1 sample), grs-alm garnets (Alm60-78Grs12-29Prp5-15) show pure dravite composition (up to 11.72 wt.% MgO) with variable prp content are typical. The prp-alm garnets with high Ti (up to 2.64 wt.% TiO2) and eventually Cr with grossular (Alm Prp Grs ) and prp-alm ones 56-58 26 15-21 (0.26 wt.% Cr2O3) contents; one detritic core belongs to (Alm77-81Prp14-17Grs2-7Sps1-7) were distinguished. Garnets schorlitic tourmaline (21 wt.% FeO). Tourmalines from contain infrequent inclusions such as rutile, quartz, the matrix of polymictic conglomerate (UD-1 sample) as and apatite. For flysch facies (GIR-1 sample), prp-sps- well as from the flysch facies (GIR-1 sample) show identical alm garnets (Alm59-63Sps20-23Prp10-14Grs4-7) and zoned characteristics. They are zoned (Figure 6c), with or without grossular-almandines (Alm65-73Grs14-24Prp8-10Sps2-3), typical an inherited core, and point to a dravitic composition of increasing almandine at the expense of the grossular (Henry et al., 2011). Their molar XMg = [Mg/(Mg + Fe)] component toward the rim, are common. Pyrope- value is in the range of 0.50 to 0.96. almandines (Alm71Prp23Grs3Sps2) are scarce. Rača Unit. Detrital tourmalines belong to the alkali- Rača Unit. There are unzoned pyrope-almandines tourmaline primary group, in which Na+ predominates 2+ (Alm74-84Prp12-17), grossular-pyrope-almandines (Alm61- (0.41–0.87 apfu) over Ca (0.0–0.26 apfu). Some inherited 70Prp19-23Grs10-16), grossular-almandines (Alm62-80Grs13-30), cores represent the calcic-tourmaline primary group, with and grossular-almandines with pyrope (Alm48Grs30Prp20) Ca2+ from 0.42 to 0.46 apfu (MRA-1, MRA-2 samples). or spessartine (Alm Grs Sps ), along with spessartine- 40 40 20 Based on the dominant divalent cations in the Y-site almandines with pyrope (Alm Sps Prp ) or 57-70 15-31 8-10 position, which are also Fe and Mg, tourmalines belong to grossular (Alm50-70Sps11-30Grs11-17). Zoned grossular- dravitic ones (Henry et al., 2011). Molar XMg = [Mg/(Mg + almandines with variation in pyrope and/or grossular Fe)] values in tourmalines range from 0.46 to 0.84. Some components (from Alm Grs Sps Prp to Alm 61 23-28 10 4-6 58- inherited cores show a schorlitic composition (MRA-2 Grs Prp Sps and from Alm Grs Prp Sps to 72 12-21 9-12 7 57 27 4 12 sample; Figure 5b). Molar X = [Mg/(Mg + Fe)] values in Alm Grs Prp Sps ), respectively, were also found. In Mg 52 40 3 5 these cores range from 0.05 to 0.35. these garnets, the Ti amount correlates positively with According to the diagram indicating the environment grossular content. They usually constitute inclusions of tourmaline origin (Henry and Guidotti, 1985), the such as ilmenite, zircon, allanite, and quartz. White mica, grains were derived from metapelites that coexisted or did chlorite, and plagioclase appear together within sps-grs not coexist with Al-rich phases, sporadically from quartz- almandine. tourmaline rocks (Figure 5b). The grains coexisting Tourmaline. Tourmaline occurs usually as short and with the Al-rich phase show low to medium content of abrupt prismatic grain, usually of brown to dark brown Ca and Ti. Schorlitic inherited cores found mainly in the colour. Rounded and subrounded tourmalines with the Mrázovce Mb. deposits originated from Li-poor granitoids, same colour are scarcer. Sharp-edged splinters were also while dravitic cores identified just in the Strihovce Fm. found. All forms noted above were found in both the Krynica and Rača units. Some tourmalines are inclusion- originated in metacarbonates and metapyroxenites or rich: quartz and zircon occurred in the RU, while quartz, Ca-poor ultramafites (Figure 5b). Unzoned tourmalines, albite, rutile, ilmenite, apatite, zircon, and titanite were typical of the Strihovce Fm., indicate origin in Al-rich found in the KU. metapelites (Henry and Guidotti, 1985). Krynica Unit. The EMP analyses show that the detrital 4.2.4. Zircon internal structure tourmalines belong to the alkali-tourmaline primary In both units, zircon forms either euhedral to subhedral group, in which Na+ predominates (0.53-0.89 apfu) over short-prismatic dipyramidal grains or long-prismatic (to Ca2+ (0.01–0.38 apfu) and K+ (<0.01 apfu). Only one grain acicular) ones without signs of corrosion (Figures 4f, 4i, (inherited core) represents the calcic-tourmaline primary and 6d–6i). Both groups are colourless, pale yellow, or group, with Ca2+ at 0.44 apfu (KOS-1 sample). Generally, pink. Rounded zircon shapes are also present. Their colour the Y-site position is dominated by Mg2+ (1.12-2.82 apfu) is the same – colourless, pink, and yellowish. Rounded and Fe2+ (up to 1.72 apfu) with subordinate content of zircons are more common in the Mrázovce Mb. deposits. 2+ Mn (0.0-0.02 apfu). Molar XMg = [Mg/(Mg + Fe)] values Krynica Unit. Following the CL images, a couple groups vary in the wide range of 0.37 to 0.99. Tourmalines from could be distinguished. For sandstone-conglomerates

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a b c

d e f

g h i

Figure 6. Representative BSE images of detrital tourmaline (a–c) and CL images of zircon (d–i) from the siliciclastics investigated: a–c) tourmaline with inherited cores from the Strihovce Fm. (KOS-1, KNC-1, UD-1 samples); d–f) internal structure of zircons from the Strihovce Fm. (KNC-1, KNC-4, GIR-1 samples); g–i) zircons from the Mrázovce Mb. deposits (MRA-2, MRA-1 samples). For detailed description see the text. facies (KNC-1, KNC-4, KOS-1 samples), the euhedral internal texture. In the flysch facies (GIR-1 sample), there to subhedral short-prismatic zircons with a concentric are zircons with convolute zoning gradually undergoing to oscillatory zoning and local marginal resorption are chaotic internal texture. It is developed in the whole grain’s characteristic (Figure 6d). Compared to the remaining profile (Figure 6f). Zircons showing concentric to regular groups, they are scarcer. The second group is represented oscillatory zoning are also present. by zircons with unzoned inherited partially resorbed Rača Unit. A few types of zircons could also be cores with a new zircon phase, “embayments”. This phase distinguished in the Mrázovce Mb. deposits: euhedral is resorbed in the final zircon growth stage by a zone grains with inclusions of ilmenite, quartz, titanite, and with irregular oscillatory zoning (Figure 6e). Zircons feldspar; drum-like zircons with acute pyramids and with recrystallised inherited cores, on which a new rounded grains. Cross-sections through zircons point to concentric to oscillatory zoned phase has grown, represent wide inner variability: zircons without or with inherited the third group. Zircons from the matrix of polymictic cores showing regular oscillatory zoning (Figure 6g); conglomerates (UD-1 sample) show regular oscillatory zircons with sector zoning; rounded zircons with patchy to zoning without local recrystallisation patterns. Some chaotic inner texture; euhedral zircons showing oscillatory zircons exhibit a sector zoning. Unzoned zircon grains zoning, which is sharply abrupt, by the growing of the indicating the first-stage rapid crystallisation represent newly formed rehomogenised phase (Figure 6h); and an individual group. A few grains show broadly reworked finally dendritic zircons (Figure 6i).

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5. Discussion Rača deposits (obtained from the panned concentrates) 5.1. Provenance of the heavy minerals was referred by Bačo et al. (2015). Summarising, there are Corrosion features of heavy minerals. The relative roughness differences in the corrosion features of HMAs between of the exterior of a grain or the facets developed on its deposits studied, indicating with all likelihood the deeper surfaces can provide information about the mechanical and burial of the Mrázovce Mb. deposits counter to the corrosion history that the detrital grain has experienced. Strihovce Fm. Faceted garnets in heavy mineral suites usually denote the Heavy mineral ratios. The HMAs show the rather dissolution after deposition (e.g., Hansley, 1987; Morton immature character of deposits studied via their low et al., 1989; Salvino and Velbel, 1989). In this case, some values of the ZTR index. The variability of garnet and heavy minerals can fully disappear. zircon surfaces denotes that the deposited heavy minerals In the HMA from the Strihovce Fm., grains almost were supplied from primary source rocks (metamorphic without corrosion signs coupled with those showing the and igneous origin), which were subjected to weathering corrosion formed during weathering (indicative of during the Eocene, and also from the recycled source rocks assumed mainly for the Mrázovce Mb. deposits. a palaeoclimatic setting) or diagenetic processes are According to provenance-sensitive heavy mineral common. Existence of weathering and unweathering ratios proposed by Morton and Hallsworth (1994, 1999), garnet surfaces simultaneously denotes their erosion both the Krynica and Rača subbasins were supplied before deposition. Faceted grains occur in sandstones with by sources of well-stocked garnet (high GZi). Despite a calcite cement. The abundance of Ca, which can act as a significant degree of corrosion on garnet surfaces, typical buffer to acid pore solutions, could control the process mainly of the Mrázovce Mb., the GZi index shows no loss of etching (Borg, 1986). An additional alternative is a of garnet due to burial. The presence of Ca-rich garnets, for resedimentation from older formations, or it may reflect instance, which are less stable than Ca-poor ones during provenance from multiple and differently weathered diagenesis (Morton, 1987; Morton and Hallsworth, 2007), sources, including bedrock of various types and maturity. also confirms this presumption. Moreover, the HMAs For the Mrázovce Mb., the shape of garnets seems to consist of ultrastable and less stable heavy minerals, which be a result of diagenesis. Postdepositional dissolution is excludes the possibility that the components more prone indicated by the absence of any evidence of abrasion on to disintegration underwent significant dissolution at the their surfaces (Figure 4g). Furthermore, the bulk grains in final deposition site or during the burial. the HMA show different degrees of diagenetic dissolution. Potential sources for detrital garnets. The elevated Indeed, the polymictic character of detrital garnet Alm content in combination with the lower Prp suggests associations and Ca-rich garnets in the HMA indicate amphibolite-facies conditions (Deer et al., 1992, 1997), that associations were not substantially modified via partially leucosomes in migmatites (Suggate and Hall, diagenetic dissolution. Therefore, they can be considered 2014). The low grossular values (<10 mol%) in the as the original and corresponding to the source rocks. The almandines are more typical of felsic rocks (gneisses scarcity of minerals such as kyanite and staurolite suggests and felsic granulites), whereas a high grossular content that they were sporadically present in the source rocks. occurs in garnets from micaschists and rocks of mafic This is consistent with the tourmaline geochemistry in the composition (amphibolites, mafic granulites). The high HMA. Rare euhedral tourmalines without any corrosion spessartine content is an indicator of igneous source rocks marks appear to be first-cycle origin from a proximate (granitoids and/or pegmatites and volcanic rocks; Deer source (MRA-2 sample), though the bulk tourmaline et al., 1997 and references therein), as well as of low-P/T grains show recycled origin. A similar situation relates the metamorphic rocks, especially those in thermal aureoles zircons. Barite derivation is debatable. Based on crystal- (Miyashiro, 1955; Deer et al., 1982; Morton et al., 2004). morphology characterisation, we speculate that abundant Heterogeneous association of detrital garnets indicates barite is diagenetic. Diagenetic barite formed in sediments their origin in different types of medium-grade metapelites is large (20–700 μm) and typically consists of flat, such as garnet micaschists, gneisses, and amphibolites tabular-shaped crystals or nodules in sedimentary layers (Figure 5a). Scarce pyrope-rich almandine garnet (Prp or mounds of porous crystals, which exhibit a layered ~28 mol%) with grossular could have originated in mafic appearance of platy crystals in diamond-shaped clusters granulites. Almandines with the Sps component may have (Paytan et al., 2002; Griffith and Paytan, 2012). Barite been derived from granites or pegmatites. Analogous from the Mrázovce Mb. deposits usually shows tabular- composition of detritic garnets was found in the Upper shaped crystals. Diagenetic barite is known from the Sub- Cretaceous-Palaeocene fms of the Krynica Unit in Poland Silesian Unit in the flysch Carpathians (Leśniak et al., (Salata, 2004). The most iron-rich almandine (87 mol% 1999). The sedimentary origin of barite distributed in the Alm) could be related to metamorphic pelitic parent

77 BÓNOVÁ et al. / Turkish J Earth Sci rocks (Deer et al., 1997). Grossular-rich almandine with composition as the hydrothermal tourmaline from the pyrope (the Mrázovce Mb.) may occur in amphibolites (l. Gemeric granite (Central Western Carpathians, Broska et c.). Garnets showing chemical zoning, where the different al., 2012). It suggests that some detrital schorlitic-dravitic distribution of Fe, Mg, Ca, and Mn via individual zones tourmaline may have been derived from granite, whereas of almandines was observed, could also be formed in fluids required for its formation come from the regional the low- to medium-grade regionally metamorphosed metamorphosis of metapelites (Jiang et al., 2008). pelitic rocks. These garnets were found in both formations Potential sources for detrital zircon. Variations in studied. Garnets showing continuously decreasing XGrs zircon colour, crystal shape, and internal zoning suggest and XSps and increasing XPrp and XAlm toward the rim a variety of source rocks. The population of elongate, suggest increasing temperature during the crystallisation euhedral zircons with oscillatory zoning points to of their rims (Spear, 1993). There are also zoned garnets significant igneous input (Vavra, 1993, 1994) into the with Ca-rich rims (Grs up to 40 mol%). The simplest Magura Basin, suggesting that deposition mainly of the interpretation for this chemical zonation of garnet is that Strihovce Fm. deposits was relatively close to an igneous the sharp increases of grossular content and Ti may reflect source. Some zircons occur as euhedral drum-like grains, successive Ca-metasomatic events, i.e. infiltration by high- sometimes with sector, convolute, or chaotic internal Ca fluids (Stowell et al., 1996). Another explanation of the structure indicating a metamorphic origin (Corfu et al., growth of grossular rims on pre-Alpine(?) garnet cores is 2003; Hoskin and Schaltegger, 2003). Complicated zoned their Alpine metamorphic overprint. This phenomenon, patterns such as truncated zoning, which is following by characteristic for metapelites and metagranitoids, is well new zircon overgrowths, are indicative for recrystallization known from the crystalline basement of the Central in the metamorphic conditions. These zircons are typical Western Carpathians (Korikovsky et al., 1990; Méres and for the Mrázovce Mb. deposits. Hovorka, 1991) and the Tisza Mega-Unit (Horváth and Provenance remarks. The HMAs and especially the Árkai, 2002), though the Grs component reached up to geochemical data of garnets well reflect the geological 30 mol% (l. c.). Extensive solid solution between grossular situation in the source areas. Chiefly garnets in both and almandine has also been found for garnets from low- formations investigated show generally similar chemical grade metamorphic rocks (Deer et al., 1997). compositions, suggesting a provenance from lithologically Potential sources for detrital tourmalines. The majority resembling source rocks. We note that the garnets with of grains display a metamorphic origin. The rather low rather high grossular content (up to 40 mol%) in the proportion of Ca and X-site vacancy in the tourmalines Mrázovce Mb. deposits were not found in the Strihovce studied suggests a medium grade of metamorphism Fm. Insufficient staurolite in the Mrázovce Mb. deposits according to Henry and Dutrow (1996). This is also may suggest the contribution from the staurolite-free supported by the relatively high Mg/Fe ratio (average 1.96 parent rocks (staurolite was found only in one gneiss and 1.66 for the KU and RU, respectively) in the bulk of pebble). The HMAs point to a provenance dominated by tourmalines, typical of the medium grade (Henry and low- to medium-grade (rarely high-grade) metamorphic Guidotti 1985). terranes including rocks of igneous origin for both units. Zoned tourmalines (with inherited cores) indicating a Although it may seem that tourmalines actually show polycyclic genesis, at which the rims are enriched by dravitic metasedimentary origin, their initial source rocks were component, denote the activity of metamorphic fluids diverse – granite (RU) versus ultramafic rock (KU). High derived from the regional metamorphosis of metapelite. concentrations of zircon are attributed to widespread low- The inherited cores that originated in metaultramafites, grade metamorphic (phyllite, micaschist) and igneous metacarbonates, or Cr-rich metasediments found in the rocks. Their euhedral shape, typical of the KU, suggests Strihovce Fm. have not been identified yet in the western the granitoid origin. The occurrence of Cr-spinels clearly part (the Biele Karpaty Unit) of the Flysch Belt (Bačo et points out a ultramafic (ophiolitic) source that had been al., 2004). This unit is considered to be a palaeogeographic feeding mainly the southern part of Magura basin (Krynica and tectonic equivalent of the Strihovce Nappe (Eastern subbasin). The Cr-spinel amount in the Mrázovce Mb. flysch zone; Potfaj in Bezák et al. 2004). Tourmalines that deposits would rather suggest that the ophiolites did not originated in igneous-hydrothermal fluids derived from deliver detritus in large quantities. granites were not found in the Strihovce Fm. Contrary to 5.2. Exotic pebble origin it, more frequent inherited cores of schorlitic composition, The diversified petrographic inventory of exotics in both which could be related to the Li-poor granitic genetic units includes the crystalline and sedimentary rocks. The environment (Henry and Guidotti, 1985), were identified pebbles known from the KU (Stráník, 1965; Wieser, 1967; in the Mrázovce Mb. deposits. The schorlitic-dravitic Nemčok et al., 1968; Marschalko et al., 1976; Mišík et al., tourmaline from granite pebbles shows a similar chemical 1991a; Oszczypko et al., 2006; Salata and Oszczypko, 2010)

78 BÓNOVÁ et al. / Turkish J Earth Sci signalise a significant lithological variability compared to and the Bohemian Massif, a similar geological development those from the RU. The determining factor for the source was suggested (Klötzli et al., 2004; Kovács et al., 2016 and area may be an absence of Silurian graptolite shales, Culm references therein). Detritus from these types of rocks sediments, Devonian and Dinantian limestones, and has not been found in the Strihovce flysch siliciclastics. Carboniferous coal (Mišík et al., 1991a), which are known Detrital garnets studied show different compositions as clasts in the external parts of the Flysch Belt (e.g., Soták, beside those from the Bohemian Massif deposits and 1985). juxtaposed units (Biernacka and Józefiak, 2009; Kowal- The rounded quartz, dark-grey siliceous rocks, Linka and Stawikowski, 2013 and references therein). They quartzites, and granites observed within the RU exotics are commonly enriched in pyrope molecule (Čopjaková et may denote their resedimentation. Poorly rounded pebbles al., 2005), typical of eclogites and/or granulites (Méres, of metamorphic rocks such as phyllite and micaschist, 2008). Certain differences are also found in the tourmaline representing the rocks with rather little stability, point composition (Biernacka, 2012 and references therein). In to transport from a relatively proximate source or consequence, the Bohemian Massif as well as the units or existence of a primary (nonrecycled) source. Eventually, terranes with a similar development may be excluded as a resedimentation of the rounded material from older potential source. formations and their mixture with local, short-distance At first sight, there are no considerable differences transported material appears to be a viable explanation. between the Mesozoic (Triassic-Jurassic) sequences of the Among crystalline pebbles found in the Mrázovce Mb. Tisza Mega-Unit (cf. Véber, 1990; Hass and Peró, 2004; deposits, there were not discovered any red orthogneiss, Vozár et al., 2010; Kovács et al., 2011) and the Strihovce limburgite and kersantite, red granite, or metalydite, which exotic pebbles of the Mesozoic age (Mišík et al., 1991a). are specific to the Strihovce Fm. (Marschalko et al., 1976); Nevertheless, first, a low-grade regional metamorphism beyond, granite with nongranitic origin of tourmaline is a connected with the Cretaceous nappe stacking within the significant mark for the Mrázovce Mb. deposits. Tisza microplate (Árkai, 2001) was not recognised in the 5.3. Palaeogeographic notices – implications for the Strihovce pebbles (Mišík et al., l. c.), albeit the Mesozoic Eocene provenance formations of the Tisza Unit were locally metamorphosed The heavy mineral analysis unambiguously confirmed only in the vicinity of the Alpine overthrusts (Árkai, 2001). a terrigenous material in the source area. It may be In the second place, there are no conodonts in the Triassic speculated about the Tisza Mega-Unit, which is made up exotic pebbles (Mišík et al., 1991a), while for the Tisza of Variscan crystalline complexes and post-Variscan – pelagic limestone facies (appearance in the Mecsek and Alpine overstep sequences. In the pre-Alpine (Variscan) Villáni units) they are known (Kovács et al., 2005, Kovács basement of the Tisza Mega-Unit the prevailing rock and Rálisch-Felgenhauer, 2005). For the Békes Unit, association consists of gneiss, micaschist, amphibolites, conodonts were not identified. It should also be mentioned and granitoids (Szederkényi et al., 2012; Haas and Buday, that the Cretaceous sequences cannot be fully paralleled. 2014). Based on the palaeogeographic position of the Tisza Although the Early Cretaceous fossil genera from the Mega-Unit during the Eocene (Csontos, 1995; Csontos Tisza Mega-Unit carbonates (Császár and Turnšek, 1996) and Vörös, 2004; Handy et al., 2014; Kováč et al., 2016), were also described in the Strihovce exotic pebbles, the palaeoflow analysis indicating the SE source (Koráb et bulk of them indicate a specific sedimentary environment al., 1962; Kováčik et al., 2011, our data), and the data unknown so far from the KU detritus. Senonian limestones dealing with its exhumation (e.g., Merten et al., 2011; until identified just from boreholes are sporadically preserved the Middle Eocene according to Kounov and Schmid, in the Tisza Mega-Unit (Császár and Haas, 1984), so they 2013), this unit could be a possible source area. Chemical could not have supplied the Krynica subbasin, which is analyses of garnets studied show similar composition to filled by Senonian limestone-bearing pebbles (Mišík et al., those from the Tisza Mega-Unit crystalline basement (cf. 1991a). Despite this, we assume that the Krynica subbasin Horváth and Árkai, 2002). Finally, monazite chemical might have been fed namely by crystalline detritus, mostly dating from exotic gneiss pebble (Poprawa et al., 2006) from the NE part (today’s coordinates) of the Tisza Mega- and exotic metapelitic rocks derived from the “southern Unit. source” (Oszczypko et al., 2016) signalise Variscan ages. Rare and exotic rocks such as red orthogneiss, On the other hand, there are serpentinite and eclogite kersantites, and limburgites represent the particularity (Baksa Complex) broadly identical to those from the of the KU pebbles (Marschalko et al., 1976). They Moldanubicum of the Bohemian Massif (Horváth et al., were interpreted as material that originated in the 2003). Following the petrological features of ultrabasic and substratum of the Magura Basin, concretely from the granitoid rocks, age, and fossil content (e.g., Silurian black North European Platform (NEP, Marschalko et al., 1976). shales), for the SW part of the Tisza crystalline basement Platform kersantites (NW Poland) show different mineral

79 BÓNOVÁ et al. / Turkish J Earth Sci compositions (Pendias and Ryka, 1974) compared to those from aforementioned units incorporated into the ravel of from the KU. The red orthogneisses often associated to the Tisza crystalline block. This block could have evolved anorthosites are known from the NEP (e.g., Cymerman, independently during the Senonian. We assume that its 2007), while anorthosite pebbles were not found in the position was not subparallel to the Pieniny Klippen Belt exotic material. “Granitic gneisses with red feldspars” were (e.g., Mišík et al., 1991a) but was rather subparallel to the identified from a drill hole within the Rzeszotary Terrane Tisza Mega-Unit realm (Figure 7). in Poland (Konior, 1974). The present basement of the KU The Marmarosh Massif, located roughly SE could be formed by the Upper Silesian Unit (USU) and/ (palaeocoordinates) from the Magura Basin during or Małopolska Terrane (MPK, Rylko and Tomaś, 2005). the Early to Middle Eocene, seems to be a potential The USU along with Brunovistulicum may continue to (longitudinal) source for clastics of crystalline origin. It the Moesia Terrane (Seghedi et al., 2005; Oczlon et al., consists of volcanites, metasediments metamorphosed in 2007; Kalvoda et al., 2008). The USU, MPK, and West a green-schist facies, gneisses, amphibolites, and granites Moesia represent a piece of Baltica-derived crust (Oczlon of Proterozoic to Palaeozoic age (Zlatogurskaja et al., 1976; et al., 2007), notwithstanding that the Małopolska Terrane Khain, 1984; Grinchenko et al., 2005). Metasedimentary partially differs from the USU (Malinowski et al., 2005). rocks commonly contain the tourmalines of schorlitic- This may indicate Late Neoproterozoic modification of the dravitic series (Szakáll et al., 2002; Matkovskyi et al., 2011) USU crust or accretion of exotic crust, now underlying and their garnets show similar geochemistry (Matkovskyi, the USU, to the southern margin of Baltica (Oczlon et al., 2009; Matkovskyi et al., 2011) as the detrital ones from the 2007). The crystalline basement of the MPK is unknown, Strihovce Fm. deposits. According to Bónová et al. (2017), while the USU constitutes the northern part of the the geochemistry of volcanic chromian spinels from the Brunovistulicum, the Precambrian basement of which Strihovce Fm. indicates that they may have been derived includes granitoids and amphibolite facies metamorphic from the Fore-Marmarosh Suture Zone (sensu Hnylko, rocks (e.g., Franke et al., 1995). On the other hand, the 2011b; Hnylko O et al., 2015). Trough Triassic deposits Rzeszotary Terrane cropping out southwards of Krakow with radiolarites that occurred in the Rachov Massif (Poland), entrained between the southern USU and MPK, (Kazintsova and Lozynyak, 1985) reveal their distinct may represent a displaced fragment of East Avalonian crust character compared to Triassic exotic pebbles from the and not form the basement to any of those (Oczlon et al., Strihovce Fm. (Mišík et al., 1991a) per quod it does not 2007). The same type of crust is cropping out in Dobrogea. promote the near position but does not exclude the origin Metamorphic formations vary in metamorphic grade from of psammitic-pelitic detritus from this source area. Such middle-upper amphibolite facies to lower greenschist detrital material could be transported via turbidite flows facies (Seghedi, 2012 and references therein). In the South from several hundred kilometres in distance. Dobrogea, the cratonic basement of the Moesian Platform Although it may seem that the Bohemian Massif was is comparable to that of the Ukrainian Shield, containing a possible source for the Rača Unit, because it was proposed Archean gneisses (Giuşcă et al., 1967; Seghedi et al., 2005). for more external zones of the Flysch Belt, much like for the This proximal Baltican terrane was displaced here along western sector of the Magura Nappe (e.g., Krystek, 1965; the Trans-European Suture Zone (Oczlon et al., 2007). Otava et al., 1997, 1998; Salata, 2014), this idea has no basis Taking into account a complicated evolution and the for the Mrázovce Mb. siliciclastics. Deficiency of rutile structure of the flysch substratum, about which we have and abundant epidote in the Culm horizonts of Drahany only poor information from the exotics and perhaps from Upland (Čopjaková et al., 2001) constituting the mixture heavy minerals, the source area for the lateral (southern) of rocks from the Bohemian Massif (Hartley and Otava, input of detritic material for the Krynica subbasin remains 2001) are an important signal for diverse sources. The enigmatic and speculative. We consider that it could amount of these minerals in the Mrázovce Fm. deposits is be a crustal segment with basement rocks (Proterozoic reversed (Figure 3). The depth of burial could have been and Palaeozoic fragments) from Caledonian terranes on an argument for epidote lack but rutile is an ultrastable the southwestern margin of the East European craton. mineral. It cannot be ascribed to resedimentation of Since the Permian time, the Outer Carpathian domain material from older strata, which could change the ratio belonging to the eastern European continental border between referenced minerals, because the tourmaline between the Bohemian Massif and the Ukrainian Shield is significantly lower in the Mrázovce Mb. deposits than was peneplenised. The Triassic sedimentary record in this in the Late Cretaceous to Palaeocene fms (cf. Salata, 2004). area is mostly unknown (Michalík, 2011). High-grade metamorphic detritus known from the Culm Summarising, the source area for lateral input referred Basin (Hartley and Otava, 2001; Čopjaková et al., 2005), to as the South-Magura Cordillera (sensu Marschalko et perhaps even from Cretaceous and Palaeogene flysch al., 1976 and Mišík et al., 1991a) could be a crustal fragment deposits of the Ukrainian Carpathians (Silesian and Skole

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W Skole - Skyba Basin Subsilesian Basine SSR

Silesian Basin SR e g - Ždánice aschber SvB W DB Fore-Magura zone Zone KR

Łabowa Fm. Mrázovce Mb. e ? EC e Rhenodanubian Beloveža Fm. MZ domain e e

VZ KrN ChN MnZ Magura realm RhN BKU MB SvN KhN e D BrN Strihovce Fm. e PK ? KmN B e e TB EA e SMR e Proč Fm. A e pu ? sen MHB Vulhovchyk Fm. i Mts.

-BZ e MZ V EV e SZ T B-CZ CWC N active subduction present active thrusting KRZ N faults and tectonic margins INZ palaeo 50° palaeotransport directions 0 50 100 km pebbles CCW rotation Figure 7. Schematic palaeogeographic situation of the Magura Basin and adjacent tectonic units during the Late Ypresian (created on the basis of own investigations and research of Koráb et al., 1962; Stránik, 1965; Contescu et al., 1966; Nemčok et al., 1968; Marschalko, 1975; Marschalko et al., 1976; Soták, 1990; Mišík et al., 1991a, 1991b; Oszczypko and Oszczypko-Clowes, 2006, 2009; Márton et al., 2007, 2013; Schmid et al., 2008; Hnylko, 2011a; Merten, 2011; Merten et al., 2011; Kováčik et al., 2011, 2012; Plašienka, 2012; Handy et al., 2014; Hnylko and Generalova, 2014; Plašienka and Soták, 2015; Hnylko O et al., 2015; Hnylko OM et al., 2015; Hnylko and Hnylko, 2016; Bónová et al., 2016, 2017; Kováč et al., 2016). MnZ – Monastyrets Zone; DB – Dukla basin, SR – Silesian Ridge, SSR – Sub-Silesian Ridge, KR – Kumane Ridge, SMR – South Magura Ridge (Cordillera); CWC – Central Western Carpathians, MHB – Myjava-Hričov Basin, EA – Eastern Alps; KhN – Kahlenberg Nappe; PKB – Pieniny Klippen Belt; BKU – Biele Karpaty Unit; INZ – Inacovce Zone; KRZ – Kricevo Zone; SZ – Szolnok Zone; T – Tisza Mega-Unit; MZ – Mecsek Zone, V-BZ – Villány-Bihor Zone, B-CZ – Békés-Codru Zone; D – Dacia Mega-Unit; TB – Transylvanian Basin (land and epicontinental area), MB – Maramures Basin (trough), VZ – Vezhany Zone; EV – Eastern Vardar ophiolitic unit; EC – Eastern Carpathians; MR – Marmarosh (Rakhov) Zone (elevation), ChN – Chornohora Nappe; SvN – Svydovets Nappe, SvB – Svydovets Basin (dipping part); KrN – Krasnoshora Nappe, Fore-Marmarosh Suture (Ceahlau): BrN – Burkut Nappe; RhN – Rakhiv Nappe, KmN – Kamyanyi Potik Nappe, W – Wien, e – emerged land. units), where it has been interpreted as a material from the and Skole units (e.g., Liszkowska and Morgiel, 2013). It Bohemian Massif (Tsymbal and Tsymbal, 2014), was not suggests along with palaeoflow directions (NW) the Fore- found in the Mrázovce Mb. deposits. Magura provenance – most probably the Silesian Ridge. In terms of palaeogeography, there could be mentioned The geological composition of the Silesian Ridge varied the fauna of “Frydek type” biofacies discovered in the from north to south (Soták, 1992; Budzyń et al., 2008, Mrázovce Mb. (Kováčik et al., 2006). This fauna is known 2011) and did not relate to the Bohemian Massif (Soták, from northern flysch nappes – Sub-Silesian, Silesian, 1990).

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6. Conclusions by the Silesian Ridge. The Marmarosh Massif (coupled Based on heavy mineral assemblages obtained here, with the Fore-Marmarosh Suture Zone) is promoted to the terrigenous crystalline material dominates in both be a longitudinal source. investigated formations. Although the heavy mineral compositions indicate that the major crystalline sources Acknowledgments for the Eocene siliciclastic formations of the Rača The research was partly supported by the project of the and Krynica units were greenschist to amphibolite Ministry of the Environment of the Slovak Republic - 0306 facies of the metamorphic rocks and granitoids, some “Geological map of the Nízke Beskydy Mts. – western part dissimilarities occurred in these suites as well as exotics at scale 1:50,000” and partially by VEGA No. 1/0963/17. suggesting the different sources. While for the Krynica The authors are thankful to J Gamcová for SEM analyses Unit we consider that the Tisza Mega-Unit crystalline and J Šašak for help in creating Figure 1a (both from complexes included a segment of the flysch substratum University of Pavol Jozef Šafárik in Košice). The authors that could represent the lateral input, the Rača Unit are also grateful to the subject editor and three anonymous might have been fed from the northern source formed reviewers for their constructive suggestions.

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